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The Effect of Freezing Drizzle, Sleet and Snow on Microphysical Characteristics of Supercooled Fog During the Icing Process in a Mountainous Area

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The Effect of Freezing Drizzle, Sleet and Snow on Microphysical Characteristics of Supercooled Fog During the Icing Process in a Mountainous Area atmosphere Article The Effect of Freezing Drizzle, Sleet and Snow on Microphysical Characteristics of Supercooled Fog during the Icing Process in a Mountainous Area Yue Zhou 1,2,*, Shengjie Niu 3, Jingjing Lü 3 and Yuehua Zhou 2 1 Hubei Key Laboratory for Heavy Rain Monitoring and Warning Research, Institute of Heavy Rain, China Meteorological Administration, Wuhan 430205, China 2 Wuhan Regional Climate Center, Wuhan 430074, China; [email protected] 3 School of Atmospheric Physics, Nanjing University of Information Science and Technology, Nanjing 210044, China; [email protected] (S.N.); [email protected] (J.L.) * Correspondence: [email protected]; Tel.: +86-27-6784-7962 Academic Editor: Robert W. Talbot Received: 20 September 2016; Accepted: 8 November 2016; Published: 11 November 2016 Abstract: Both the similar and different effects of freezing drizzle, sleet and snow on microphysical properties of supercooled fog were analyzed for fourteen events during a comprehensive wire icing, fog, and precipitation observation experiment conducted at Enshi radar station (30◦170N, 109◦160E; 1722 m a.s.l.) on a hilltop in Shibanling, Hubei, China. Liquid precipitation is in a relatively stable form in mountainous areas. Short-term precipitation (1–3 h) is dominant with temperature below 0 ◦C. The wet scavenging effect of freezing drizzle on small fog droplets with a size range less than 6–12 µm is weak but is stronger for fog droplets with a larger size, which is opposite to the effects of solid precipitation, broadening the fog droplet spectra significantly. As the fog droplet diameter increases, the distributions of droplet spectra change from leptokurtosis to platykurtosis and from positive skewness to negative skewness. Occurrence of freezing drizzle would improve the positive correlation of N-r in dissipation and oscillation periods, resulting in the N-r relationship having a weak negative correlation in the maturity period, and resulting in the transition of the N-L and N-r relationships into positive correlations in the development period. Meanwhile, the emergence of solid precipitation particles would result in negative values for the correlation coefficients of N-L and N-r. The change in relationships among the microphysical properties was caused by the occurrence of different phase precipitation, showing the influence on the main microphysical mechanisms of supercooled fog. Keywords: supercooled fog; different phase precipitation; similar and different effects; microphysical characteristics; mountainous area 1. Introduction Mountainous areas, due to their rich water vapor and low temperature, are prone to icing processes (glaze, rime and wet snow, etc.) [1]. These areas are usually preferred for high-voltage transmission line construction because of their characteristics, e.g., considerable land area and few people. However, long-term icing in mountainous areas caused by supercooled cloud/fog and precipitation seriously affects the security of transmission lines, resulting in disaster accidents, such as tower collapse, line breakage, flashover and fitting destruction [2,3], and threatening the normal operation of people's daily lives and production activities, especially in mountainous areas in winter [4]. A freezing rain and snow event in 2008 caused the collapse of 172,000 high-voltage towers, the breakage of 129,000 high-voltage lines, and the outage of 884 substations. Of these incidents, the towers at an altitude of over 300 meters accounted for 53.1% of the total collapsed towers [5,6]. High wind speed Atmosphere 2016, 7, 143; doi:10.3390/atmos7110143 www.mdpi.com/journal/atmosphere Atmosphere 2016, 7, 143 2 of 17 throughout the year has resulted in mountainous areas becoming the main distribution area for wind turbine generator systems [7,8]. The icing process exerts a more significant effect on wind power generation, as a severe icing disaster will not only significantly reduce power generation efficiency but also damage blades, leading to the stoppage of the generator. Even weak icing processes will change the aerodynamic characteristics of the blades, thereby lowering electricity generation expectation [9]. During the icing process, supercooled droplets hit the object surface, forming a transparent or an opaque glassy ice layer, which can be mainly divided into precipitation icing and in-cloud icing [10,11]. Precipitation icing often occurs in plains [12,13], where freezing drizzle and wet snow occur in medium-high altitude mountains and usually last a short time [14,15]; in-cloud icing is an icing process caused by cloud or fog in a supercooled state, which takes place in the mountains with a longer duration [9,16,17]. Irrespective of the icing process (except wet snow icing), what determines icing intensity is the mass of supercooled liquid water per unit volume, supercooled droplet size and the duration of the process [18,19]. Therefore, it is very important to explore macro and micro characteristics of fog and precipitation during the icing process in mountainous areas. In recent years, studies on fog macro and micro characteristics mainly focused on the Yangtze River Delta and Pearl River Delta areas and centered on aspects such as the temporal and spatial variation of fog, temperature and humidity distribution, physical and chemical characteristics, remote sensing and numerical simulation research conducted in China [20–26]. However, the macro and micro characteristics of the mountain fog process have been paid little attention by scholars. Compared to plain areas, the abundant moisture in mountainous areas is more conducive to the fog process formation [27], as the uplift of warm moist air by mountain wind circulation easily results in saturation, which causes the formation of fog [28]. Tang et al. [29] and Wu et al. [30] found that fog in Dayaoshan Mountain was mainly advection and upslope fog, and fog on the windward slope was stronger than that on the leeward slope. The fog droplet concentration of mountainous fog is generally 102 cm−3 in China, which is between the values for city fog (102–103 cm−3) and sea fog (101–102 cm−3); the liquid water content is generally 0.1–0.2 g·m−3; average diameter is about 10 µm, all of which are significantly lower than those of fog in other regions [31], though its duration is significantly longer than other types of fog [32]. Deng et al. [33] noted that the fog process in Nanling Mountain is a small-droplet pattern; the particle size of most droplets is less than 12 µm, and advection factors and terrain effects have a major impact on the fluctuant changes in microphysical properties. Hilltop fog is mainly caused by a cloud system after cold front transit. Under advection, a hilltop is more vulnerable to a strong and stable fog process compared to a slope [34–36]. Similarly, the number concentration, liquid water content and average diameter of mountain fog in Guizhou province are 234 cm−3, 0.2 g·m−3 and 7.5 µm, respectively. The fog has a peak diameter of 4 µm, with a peak concentration of approximately 63% of total concentration [37]. However, with an adequate supply of water vapor, there would be a significant increase in the liquid water content of mountain fog [38]. Drage and Hauge [5] observed and simulated the liquid water content of supercooled fog in coastal mountain areas and showed that the liquid water content reached 0.4 g·m−3 during a rapid growth period of icing. However, the fog process in mountainous areas usually does not occur alone in winter but is often accompanied by freezing precipitation [39]. There are usually two formation mechanisms of freezing precipitation: melting process and supercooled warm rain process. The melting process mainly occurs in plains, which is the main mechanism for the formation of freezing rain [13], while the supercooled warm rain process primarily occurs in high altitude areas or mountains, which is the main mechanism for the formation of freezing drizzle [40]. The supercooled warm rain process does not require the presence of a warm layer above 0 ◦C over the observation point. The diameters of supercooled droplets increase through collision-coalescence mechanisms and fall to the ground in the form of freezing drizzle [41,42]. Hilltop observation points, due to their high altitude, are vulnerable to exposure to the bottom of the cloud formed after cold front transit. In an environment of high relative humidity at low levels, under stably stratified conditions, weak mesoscale uplift, cloud tops of −15 ◦C Atmosphere 2016, 7, 143 3 of 17 or warmer, and low concentrations of both ice crystals and ice nuclei, the formation of freezing drizzle would be more favorable [43]. In comprehensive observations of macro and micro characteristics of wire icing during the winter of 2009 and 2010, we observed the simultaneous occurrence of supercooled fog and freezing drizzle, mixed-phase precipitation or solid precipitation several times when icing occurred. Precipitation would have some “scouring action” on the fog process and would reduce the liquid water content of fog, but increased moisture due to precipitation particle evaporation is beneficial to the maintenance of fog [44]. In particular, when solid precipitation occurs, under the effect of ice crystals, the growth of ice particles will consume the supercooled fog droplets [45], thereby affecting the microphysical properties of supercooled fog. However, observational experiments and numerical simulations have mostly focused on pure foggy weather; there is less research on the phenomena
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